juli ashton : This Is An Un Official Fan Site Tribute
Julie Astin, Juli Austin, Juli Aston & Julie Austin Julie Astin, Juli Austin, Juli Aston, Julie Austin, Juli Astin
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juli ashton

PERFORMER AKA Julie Astin, Juli Austin, Juli Aston, Julie Austin, Juli Astin DIRECTOR AKA No known aliases BIRTHDAY October 05, 1969 (50 years old) ASTROLOGY Libra BIRTHPLACE Colorada Springs, CO YEARS ACTIVE AS PERFORMER 1994-2005 (Started around 25 years old) YEARS ACTIVE AS DIRECTOR 1997-2001
Juli Ashton (born October 5, 1969) is an American former pornographic actress. Contents 1 Adult film career 2 Awards 3 References 4 External links Adult film career In 1994, she moved to Florida and began appearing in adult films, starting with New Wave Hookers 4. From 1996 to 2006 she was co-host of the Playboy Channel's live phone-in program Night Calls. In addition to her film and television work, she has lobbied on behalf of the adult industry at the California State Legislature. Juli is the owner and operator of the adult website Juliland.com, a website that features the erotic imagery of photographer/director Richard Avery.



Awards 1996 XRCO Award – Female Performer of the Year 1997 AVN Award – Best Supporting Actress—Video (Head Trip) 2000 NightMoves Award – Best Actress (Editor's Choice) 2011 XRCO Hall of Fame 2012 AVN Hall of Fame 1997 Apago NonSex 1 Adult Affairs 1995 VCA Anal Facial 1 Adventures In Paradise 5 1998 Klimaxxx Productions Anal Anarchy 1996 VCA Anal DP DO Anal Candy Ass 1994 Rosebud Anal Facial A2M 2 DO Anal Deep Rider 1995 Rosebud Anal Facial 1 DO Anal Island 1 1996 VCA Anal 1 Anal Island 2 1996 VCA Anal Facial 1 Attitude 1995 VCA 2 D Babenet 1995 VCA NonSex 1 Bald Beaver Blast 2005 VCA 1 D Bare Essentials 1995 NightVision NonSex O Basically Becca 2001 Wicked Pictures LezOnly 3 DRO Basically Julia Ann And Becca Too 2000 Wicked Pictures 1 Being With Juli Ashton 2000 VCA Anal Facial DP IR 7 DR Best Friends 2000 VCA Anal Facial 3 DRO Black Boots 1999 VCA IR 2 DRO Bliss 1999 VCA Anal 9 DRO Blonde Legends 2007 Wicked Pictures DRO Bone Appetite 2003 Sin-X DO Brassiere To Eternity 1994 Pepper Productions LezOnly 1 Buried Treasure 2000 Wicked Pictures Anal Facial Butt Detective 1995 VCA Anal Facial 10 DRO Butt Motors 1996 VCA LezOnly Car Wash Angels 1 1996 VCA Facial IR 2 DO Conquest 1996 Wicked Pictures Anal Facial 16 DRO Consenting Adults 2000 Wicked Pictures 1 DRO Convention Cuties 1997 Southern Shore NonSex 1 Corporate Assets 2 1997 Adam & Eve Facial 1 DRO Cuntrol 1994 Midnight Video LezOnly 1 D Cyberanal 1996 VCA Anal 3 DRO Danni's Wet Adventures 2003 danni.com NonSex O Dark Garden 1999 VCA Anal 4 DRO Darling 1999 Wicked Pictures Anal DO Daydreams Nightdreams 1997 VCA 1 DRO Deep Inside Asia Carrera 1997 VCA Facial 1 DRO Deep Inside Felecia 1997 VCA LezOnly 1 DRO Deep Inside Juli Ashton 1996 VCA Anal Facial DP 1 DRO Deep Inside Kylie Ireland 1999 VCA LezOnly 1 DRO Deep Inside Missy 1997 VCA LezOnly 1 DRO Deep Inside Misty Rain 1996 VCA LezOnly 3 DRO Deep Inside Nina Hartley 2 1999 VCA LezOnly Clip DRO Deep Inside Shayla LaVeaux 1997 VCA Facial 1 DRO Deep Seven 1996 VCA Anal Facial 1 DRO Devil in Miss Jones 5 1995 VCA Anal Facial 5 DRO Devil in Miss Jones 6 1999 VCA Anal 7 DRO Dinner Party 1 1994 Adam & Eve LezOnly 4 DRO Dirty Bob's Xcellent Adventures 30 1997 Flying Leap Productions NonSex 1 Dirty Bob's Xcellent Adventures 31 1997 Flying Leap Productions NonSex 1 Dirty Bob's Xcellent Adventures 37 1997 Flying Leap Productions NonSex 1 Dirty Dyanna 1996 Midnight Video Diva 1: Caught in the Act 1997 VCA LezOnly 2 DRO Diva Girls 1999 VCA MastOnly 5 DRO Double Dippin 2003 Adam & Eve NonSex 1 DRO Double Stuffed Creampuffs 2008 Filth Factory D Erotic Seduction 2002 Alexander Institute DRO Essentially Dee (and Juli Too) 1999 Wicked Pictures Anal Facial Bald IR 2 Essentially Juli 1997 Wicked Pictures Anal Facial IR 4 O Essentially Shayla (and Juli Too) 1999 Wicked Pictures Anal Facial 1 D Every Woman Has A Fantasy 3 1995 VCA Anal Facial 3 DRO Fade to Blue 1998 VCA Anal Facial DP IR 7 DRO Film Buff 1994 Wicked Pictures LezOnly 6 DRO Fluffy Cumsalot, Porn Star 2002 United Nathan NonSex Fountain of Innocence 1997 VCA Anal Facial DP 1 DRO Fucking Assholes 2003 VCA DO Gangland Bangers 1996 VCA Anal Facial 1 DR Girl Next Door 2000 Indican Pictures NonSex 1 DRO Happy Assed Lesbians 1995 Rosebud LezOnly Head Trip 1996 VCA Anal DP 1 DO Heat 1 2002 Adam & Eve DRO I Kissed A Girl 2009 Wicked Pictures LezOnly DRO Interracial Classics 2019 VCA DO Kink Club 1 2002 Adam & Eve 1 DRO Latex 1995 VCA Anal Facial 7 DRO Lesbian Bitches 1994 Rosebud LezOnly 1 Lettin' Her Fingers Do The Walking 2005 Wicked Pictures MastOnly DRO Love's Passion 1998 VCA Anal 4 DO Lust In Space 1998 VCA DR Masque 1996 VCA Anal Facial DP IR 1 DRO Max World 19: Cities On Flame 1999 Legend Video NonSex 1 Maxed Out 6 1997 Legend Video NonSex 1 O Mutual Consent 1995 VCA 1 My First Porno 2000 Wicked Pictures NonSex 1 DO Naked Ambition 1995 VCA Facial 1 New Wave Hookers 4 1994 VCA Anal Facial 3 DRO New Wave Hookers 5 1997 VCA Anal Facial 9 DRO New Years Sleaze 2008 Wicked Pictures DO Nightshift Nurses 2 1996 VCA Anal Facial 1 DRO Older Women Hotter Sex 2000 VCA LezOnly IR 1 Once In A Lifetime 1996 VCA Other Woman 1996 VCA Facial Bald DO Pajama Party X 3 1994 VCA Facial 1 DO Passion in Venice 1995 Adam & Eve Facial 5 DRO Pleasure Bound 1997 Dreamland Video Pleasure Pit 1998 VCA D Pubic Access 1995 VCA Facial 1 O Pussy Lickin Good 2004 VCA LezOnly DRO Queen Of Smut 1999 VCA Anal Bald 1 DRO Scarlet Woman 1995 Wicked Pictures Anal Facial DP 2 DRO Scotty's X-rated Adventure 1996 Wicked Pictures Anal Facial DP 1 DO Plate tectonics (from the Late Latin: tectonicus, from the Ancient Greek: te?t??????, lit. 'pertaining to building')[1] is a scientific theory describing the large-scale motion of seven large plates and the movements of a larger number of smaller plates of the Earth's lithosphere, since tectonic processes began on Earth between 3.3[2] and 3.5 billion years ago. The model builds on the concept of continental drift, an idea developed during the first decades of the 20th century. The geoscientific community accepted plate-tectonic theory after seafloor spreading was validated in the late 1950s and early 1960s. The lithosphere, which is the rigid outermost shell of a planet (the crust and upper mantle), is broken into tectonic plates. The Earth's lithosphere is composed of seven or eight major plates (depending on how they are defined) and many minor plates. Where the plates meet, their relative motion determines the type of boundary: convergent, divergent, or transform. Earthquakes, volcanic activity, mountain-building, and oceanic trench formation occur along these plate boundaries (or faults). The relative movement of the plates typically ranges from zero to 100 mm annually.[3] Tectonic plates are composed of oceanic lithosphere and thicker continental lithosphere, each topped by its own kind of crust. Along convergent boundaries, subduction, or one plate moving under another, carries the lower one down into the mantle; the material lost is roughly balanced by the formation of new (oceanic) crust along divergent margins by seafloor spreading. In this way, the total surface of the lithosphere remains the same. This prediction of plate tectonics is also referred to as the conveyor belt principle. Earlier theories, since disproven, proposed gradual shrinking (contraction) or gradual expansion of the globe.[4] Tectonic plates are able to move because the Earth's lithosphere has greater mechanical strength than the underlying asthenosphere. Lateral density variations in the mantle result in convection; that is, the slow creeping motion of Earth's solid mantle. Plate movement is thought to be driven by a combination of the motion of the seafloor away from spreading ridges due to variations in topography (the ridge is a topographic high) and density changes in the crust (density increases as newly formed crust cools and moves away from the ridge). At subduction zones the relatively cold, dense oceanic crust is "pulled" or sinks down into the mantle over the downward convecting limb of a mantle cell.[5] Another explanation lies in the different forces generated by tidal forces of the Sun and Moon. The relative importance of each of these factors and their relationship to each other is unclear, and still the subject of much debate. Contents 1 Key principles 2 Types of plate boundaries 3 Driving forces of plate motion 3.1 Driving forces related to mantle dynamics 3.2 Driving forces related to gravity 3.3 Driving forces related to Earth rotation 3.4 Relative significance of each driving force mechanism 4 Development of the theory 4.1 Summary 4.2 Continental drift 4.3 Floating continents, paleomagnetism, and seismicity zones 4.4 Mid-oceanic ridge spreading and convection 4.5 Magnetic striping 4.6 Definition and refining of the theory 4.7 Plate Tectonics Revolution 5 Implications for biogeography 6 Plate reconstruction 6.1 Defining plate boundaries 6.2 Past plate motions 6.3 Formation and break-up of continents 7 Current plates 8 Other celestial bodies (planets, moons) 8.1 Venus 8.2 Mars 8.3 Icy satellites 8.4 Exoplanets 9 See also 10 References 10.1 Citations 10.2 Sources 11 External links Key principles The outer layers of the Earth are divided into the lithosphere and asthenosphere. The division is based on differences in mechanical properties and in the method for the transfer of heat. The lithosphere is cooler and more rigid, while the asthenosphere is hotter and flows more easily. In terms of heat transfer, the lithosphere loses heat by conduction, whereas the asthenosphere also transfers heat by convection and has a nearly adiabatic temperature gradient. This division should not be confused with the chemical subdivision of these same layers into the mantle (comprising both the asthenosphere and the mantle portion of the lithosphere) and the crust: a given piece of mantle may be part of the lithosphere or the asthenosphere at different times depending on its temperature and pressure. The key principle of plate tectonics is that the lithosphere exists as separate and distinct tectonic plates, which ride on the fluid-like (visco-elastic solid) asthenosphere. Plate motions range up to a typical 10–40 mm/year (Mid-Atlantic Ridge; about as fast as fingernails grow), to about 160 mm/year (Nazca Plate; about as fast as hair grows).[6] The driving mechanism behind this movement is described below. Tectonic lithosphere plates consist of lithospheric mantle overlain by one or two types of crustal material: oceanic crust (in older texts called sima from silicon and magnesium) and continental crust (sial from silicon and aluminium). Average oceanic lithosphere is typically 100 km (62 mi) thick;[7] its thickness is a function of its age: as time passes, it conductively cools and subjacent cooling mantle is added to its base. Because it is formed at mid-ocean ridges and spreads outwards, its thickness is therefore a function of its distance from the mid-ocean ridge where it was formed. For a typical distance that oceanic lithosphere must travel before being subducted, the thickness varies from about 6 km (4 mi) thick at mid-ocean ridges to greater than 100 km (62 mi) at subduction zones; for shorter or longer distances, the subduction zone (and therefore also the mean) thickness becomes smaller or larger, respectively.[8] Continental lithosphere is typically about 200 km thick, though this varies considerably between basins, mountain ranges, and stable cratonic interiors of continents. The location where two plates meet is called a plate boundary. Plate boundaries are commonly associated with geological events such as earthquakes and the creation of topographic features such as mountains, volcanoes, mid-ocean ridges, and oceanic trenches. The majority of the world's active volcanoes occur along plate boundaries, with the Pacific Plate's Ring of Fire being the most active and widely known today. These boundaries are discussed in further detail below. Some volcanoes occur in the interiors of plates, and these have been variously attributed to internal plate deformation[9] and to mantle plumes. As explained above, tectonic plates may include continental crust or oceanic crust, and most plates contain both. For example, the African Plate includes the continent and parts of the floor of the Atlantic and Indian Oceans. The distinction between oceanic crust and continental crust is based on their modes of formation. Oceanic crust is formed at sea-floor spreading centers, and continental crust is formed through arc volcanism and accretion of terranes through tectonic processes, though some of these terranes may contain ophiolite sequences, which are pieces of oceanic crust considered to be part of the continent when they exit the standard cycle of formation and spreading centers and subduction beneath continents. Oceanic crust is also denser than continental crust owing to their different compositions. Oceanic crust is denser because it has less silicon and more heavier elements ("mafic") than continental crust ("felsic").[10] As a result of this density stratification, oceanic crust generally lies below sea level (for example most of the Pacific Plate), while continental crust buoyantly projects above sea level (see the page isostasy for explanation of this principle). Types of plate boundaries Main article: List of tectonic plate interactions Three types of plate boundaries exist,[11] with a fourth, mixed type, characterized by the way the plates move relative to each other. They are associated with different types of surface phenomena. The different types of plate boundaries are:[12][13] Divergent boundary Convergent boundary Transform boundary Divergent boundaries (Constructive) occur where two plates slide apart from each other. At zones of ocean-to-ocean rifting, divergent boundaries form by seafloor spreading, allowing for the formation of new ocean basin. As the ocean plate splits, the ridge forms at the spreading center, the ocean basin expands, and finally, the plate area increases causing many small volcanoes and/or shallow earthquakes. At zones of continent-to-continent rifting, divergent boundaries may cause new ocean basin to form as the continent splits, spreads, the central rift collapses, and ocean fills the basin. Active zones of mid-ocean ridges (e.g., the Mid-Atlantic Ridge and East Pacific Rise), and continent-to-continent rifting (such as Africa's East African Rift and Valley and the Red Sea), are examples of divergent boundaries. Convergent boundaries (Destructive) (or active margins) occur where two plates slide toward each other to form either a subduction zone (one plate moving underneath the other) or a continental collision. At zones of ocean-to-continent subduction (e.g. the Andes mountain range in South America, and the Cascade Mountains in Western United States), the dense oceanic lithosphere plunges beneath the less dense continent. Earthquakes trace the path of the downward-moving plate as it descends into asthenosphere, a trench forms, and as the subducted plate is heated it releases volatiles, mostly water from hydrous minerals, into the surrounding mantle. The addition of water lowers the melting point of the mantle material above the subducting slab, causing it to melt. The magma that results typically leads to volcanism.[14] At zones of ocean-to-ocean subduction (e.g. Aleutian islands, Mariana Islands, and the Japanese island arc), older, cooler, denser crust slips beneath less dense crust. This motion causes earthquakes and a deep trench to form in an arc shape. The upper mantle of the subducted plate then heats and magma rises to form curving chains of volcanic islands. Deep marine trenches are typically associated with subduction zones, and the basins that develop along the active boundary are often called "foreland basins". Closure of ocean basins can occur at continent-to-continent boundaries (e.g., Himalayas and Alps): collision between masses of granitic continental lithosphere; neither mass is subducted; plate edges are compressed, folded, uplifted. Transform boundaries (Conservative) occur where two lithospheric plates slide, or perhaps more accurately, grind past each other along transform faults, where plates are neither created nor destroyed. The relative motion of the two plates is either sinistral (left side toward the observer) or dextral (right side toward the observer). Transform faults occur across a spreading center. Strong earthquakes can occur along a fault. The San Andreas Fault in California is an example of a transform boundary exhibiting dextral motion. Plate boundary zones occur where the effects of the interactions are unclear, and the boundaries, usually occurring along a broad belt, are not well defined and may show various types of movements in different episodes. Driving forces of plate motion Plate motion based on Global Positioning System (GPS) satellite data from NASA JPL. Each red dot is a measuring point and vectors show direction and magnitude of motion. It has generally been accepted that tectonic plates are able to move because of the relative density of oceanic lithosphere and the relative weakness of the asthenosphere. Dissipation of heat from the mantle is acknowledged to be the original source of the energy required to drive plate tectonics through convection or large scale upwelling and doming. The current view, though still a matter of some debate, asserts that as a consequence, a powerful source of plate motion is generated due to the excess density of the oceanic lithosphere sinking in subduction zones. When the new crust forms at mid-ocean ridges, this oceanic lithosphere is initially less dense than the underlying asthenosphere, but it becomes denser with age as it conductively cools and thickens. The greater density of old lithosphere relative to the underlying asthenosphere allows it to sink into the deep mantle at subduction zones, providing most of the driving force for plate movement. The weakness of the asthenosphere allows the tectonic plates to move easily towards a subduction zone.[15] Although subduction is thought to be the strongest force driving plate motions, it cannot be the only force since there are plates such as the North American Plate which are moving, yet are nowhere being subducted. The same is true for the enormous Eurasian Plate. The sources of plate motion are a matter of intensive research and discussion among scientists. One of the main points is that the kinematic pattern of the movement itself should be separated clearly from the possible geodynamic mechanism that is invoked as the driving force of the observed movement, as some patterns may be explained by more than one mechanism.[16] In short, the driving forces advocated at the moment can be divided into three categories based on the relationship to the movement: mantle dynamics related, gravity related (main driving force accepted nowadays), and earth rotation related. Driving forces related to mantle dynamics Main article: Mantle convection For much of the last quarter century, the leading theory of the driving force behind tectonic plate motions envisaged large scale convection currents in the upper mantle, which can be transmitted through the asthenosphere. This theory was launched by Arthur Holmes and some forerunners in the 1930s[17] and was immediately recognized as the solution for the acceptance of the theory as originally discussed in the papers of Alfred Wegener in the early years of the century. However, despite its acceptance, it was long debated in the scientific community because the leading theory still envisaged a static Earth without moving continents up until the major breakthroughs of the early sixties. Two- and three-dimensional imaging of Earth's interior (seismic tomography) shows a varying lateral density distribution throughout the mantle. Such density variations can be material (from rock chemistry), mineral (from variations in mineral structures), or thermal (through thermal expansion and contraction from heat energy). The manifestation of this varying lateral density is mantle convection from buoyancy forces.[18] How mantle convection directly and indirectly relates to plate motion is a matter of ongoing study and discussion in geodynamics. Somehow, this energy must be transferred to the lithosphere for tectonic plates to move. There are essentially two main types of forces that are thought to influence plate motion: friction and gravity. Basal drag (friction): Plate motion driven by friction between the convection currents in the asthenosphere and the more rigid overlying lithosphere. Slab suction (gravity): Plate motion driven by local convection currents that exert a downward pull on plates in subduction zones at ocean trenches. Slab suction may occur in a geodynamic setting where basal tractions continue to act on the plate as it dives into the mantle (although perhaps to a greater extent acting on both the under and upper side of the slab). Lately, the convection theory has been much debated, as modern techniques based on 3D seismic tomography still fail to recognize these predicted large scale convection cells.[citation needed] Alternative views have been proposed Screen Play 1998 Wicked Pictures Anal IR 1 D Secret Lives of Porn Stars 2005 Xenon Pictures NonSex Sex Ahoy 2005 Wicked Pictures DRO Shave the 90s 2019 VCA DO Shayla's Swim Party 1996 VCA NonSex Shock: Latex 2 1996 VCA LezOnly 3 DO Shower Head 2006 VCA DO Smells Like... Sex 1996 VCA Anal Facial DP 1 DRO Sorority Sex Kittens 3 1996 VCA LezOnly 5 DRO Still Insatiable 1998 VCA 10 DO Sunrise To Sunset 2006 VCA DO Super Stud Spectacular: Tom Byron 2012 VCA DO Torn 1999 VCA LezOnly 8 DO Toys For Great Sex 2000 Alexander Institute LezOnly 1 DR Triple X 12 1996 Private NonSex 1 DRO Trollin' For Trouser Trout 2007 VCA DO Twist Of Fate 1996 Wicked Pictures LezOnly 6 DO Under The Pink 1994 Rosebud LezOnly 1 DO Virgin Porn Stars 3 2003 VCA DO Vortex 1998 VCA Anal Facial 5 DR Wide Open Spaces 1995 VCA LezOnly 5 DRO Women Loving Women: A Guide to Sapphic Lovemaking Techniques 2005 VCA D Wrong Snatch 1998 VCA Facial 3 DRO XRCO Awards 1998 1998 Wicked Pictures NonSex


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